Methods and systems to separate wavefields using pressure wavefield data

ABSTRACT

This disclosure is directed to wavefield separation methods and systems. In one aspect, methods and systems compute an approximate vertical particle velocity wavefield based on a measured pressure wavefield and knowledge of free-surface when the pressure wavefield was measured. The measured pressure wavefield is used to compute an approximate frozen free-surface profile. The approximate frozen free-surface profile and the measured pressure wavefield are used to compute an approximate vertical particle velocity wavefield. The approximate vertical particle velocity wavefield and measured pressure wavefield may be used to compute separate up-going and down-going pressure, or vertical particle velocity, wavefields.

CROSS-REFERENCE TO RELATED APPLICATION

This application claims the benefit of Provisional Application No.61/981,166 on Apr. 17, 2014.

BACKGROUND

In recent years, the petroleum industry has invested heavily in thedevelopment of improved marine survey techniques and seismic dataprocessing methods in order to increase the resolution and accuracy ofseismic images of subterranean formations. Marine surveys illuminate asubterranean formation located beneath a body of water with acousticsignals produced by one or more submerged seismic sources. The acousticsignals travel down through the water and into the subterraneanformation. At interfaces between different types of rock or sediment ofthe subterranean formation a portion of the acoustic signal energy maybe refracted, a portion may be transmitted, and a portion may bereflected back toward the formation surface and into the body of water.A typical marine survey is carried out with a survey vessel that passesover the illuminated subterranean formation while towing elongatedcable-like structures called streamers. The streamers may be equippedwith a number of collated, dual pressure and particle motion sensorsthat detect pressure and vertical particle motion wavefields,respectively, associated with the acoustic signals reflected back intothe water from the subterranean formation. The pressure sensors generateseismic data that represents the pressure wavefield and the particlemotion sensors generate seismic data that represents the verticalparticle motion wavefield. The survey vessel receives and records theseismic data generated by the sensors.

A wavefield that travels upward from the subterranean formation and isdetected by the pressure or particle motion sensors is called anup-going wavefield, which alone may be used to compute a seismic imageof the subterranean formation. However, the surface of the water acts asa nearly perfect acoustic reflector. As a result, the sensors alsodetect a down-going wavefield created by reflection of the up-goingwavefield from the water surface. The down-going wavefield isessentially the up-going wavefield with a time delay that corresponds tothe amount of time it takes for acoustic signals to travel up past thestreamers to the water surface and back down to the streamers. Thedown-going wavefield combines with the up-going wavefield, resulting inrecorded seismic data contaminated with, unwanted down-going wavefieldenergy that creates “ghost” effects in seismic images of thesubterranean formation computed from the seismic data. Typical seismicdata processing techniques use both the pressure wavefield and verticalparticle motion wavefield to separate the pressure and vertical particlemotion wavefields into up-going and down-going wavefields. The up-goingwavefield may be used to compute an image of a subterranean formationwithout the ghost effects caused by the down-going wavefield.

DESCRIPTION OF THE DRAWINGS

FIGS. 1A-1B show side-elevation and top views, respectively, of anexample seismic data acquisition system.

FIG. 2 shows a side-elevation view of a seismic data acquisition systemwith a magnified view of a receiver.

FIG. 3 shows example ray paths that represent paths of an acousticsignal that travels from a source into a subterranean formation.

FIG. 4 shows a plot of a synthetic common-shot gather composed ofexample traces.

FIG. 5 shows an example expanded view of a synthetic gather composed of38 traces.

FIGS. 6A-6C show an overview of how a measured pressure wavefield may beseparated into up-going and down-going pressure wavefields.

FIG. 7 shows a side-elevation view of a streamer located in a body ofwater below a frozen free-surface.

FIG. 8 shows a streamer, a frozen free-surface, and an example series oftrial depths.

FIG. 9 shows an example of forward and backward extrapolated pressurewavefield at a trial depth.

FIG. 10 shows a series of forward extrapolated gathers and correspondingbackward extrapolated gathers for a series of trial depths.

FIG. 11 shows difference gathers computed from pairs of forward andbackward extrapolated gathers shown in FIG. 10.

FIGS. 12A-12C show an example calculation of a maximum energy differencefor a series of time windows.

FIG. 13 shows the time windows applied to difference gathers associatedwith different trial depths.

FIG. 14 shows a side-elevation view of a set of points above receiversthat approximate a frozen free-surface.

FIG. 15 shows an example calculation of amplitude differences for twoseparate time windows.

FIG. 16A shows a side-elevation view of a streamer, a frozenfree-surface, and an approximate frozen free-surface profile.

FIG. 16B shows a plot of an extended portion of the approximate frozenfree-surface profile shown in FIG. 16A.

FIG. 17 shows a plot of frozen free-surface wavefield reflectivityparameters.

FIGS. 18A-18B shows example side-elevation views of a source depthrelative to streamer depth.

FIG. 19 shows a segment of a streamer located beneath an approximatefrozen free-surface profile.

FIG. 20 shows a flow-control diagram of a method that computes separatedwavefields from measured pressure wavefields.

FIG. 21 shows a flow-control diagram of the routine “compute maximumenergy difference” called in block 2010 of FIG. 20.

FIG. 22 shows a flow-control diagram of the routine “wavefieldseparation” called in block 2015 of FIG. 20.

FIG. 23 shows a flow-control diagram of the routine “compute verticalparticle velocity wavefield” called in block 2209 of FIG. 23.

FIG. 24A-24B show flow-control diagrams of a method that computesseparated wavefields from measured pressure wavefields.

FIG. 25 shows an example of a computer system programmed to executeefficient methods of computing approximate vertical particle velocitywavefields.

FIGS. 26A-26B show simulation results in calculating an approximation toa frozen free-surface.

DETAILED DESCRIPTION

This disclosure is directed to methods and systems that performwavefield separation. The methods and systems compute an approximatevertical particle velocity wavefield based on a measured pressurewavefield and knowledge of a free-surface when the pressure wavefieldwas measured. The measured pressure wavefield is used to compute anapproximate frozen free-surface profile of the free-surface. Theapproximate frozen free-surface profile and the measured pressurewavefield are used to compute an approximate vertical particle velocitywavefield. The approximate vertical particle velocity wavefield andmeasured pressure wavefield may be used to compute separate up-going anddown-going pressure wavefields or vertical particle velocity wavefields.The up-going pressure wavefield or vertical particle velocity wavefieldmay, in turn, be used to compute seismic images with significantlyhigher resolution and deeper signal penetration than seismic imagescomputed with seismic data contaminated with the down-going wavefield.Removal of the effects of the down-going wavefield may reduce unwantednoise during marine surveying or reservoir production monitoring.

FIGS. 1A-1B show side-elevation and top views, respectively, of anexample seismic data acquisition system composed of a survey vessel 102towing a source 104 and six separate streamers 106-111 beneath afree-surface 112 of a body of water. The body of water may be, forexample, an ocean, a sea, a lake, or a river, or any portion thereof. Inthis example, each streamer is attached at one end to the survey vessel102 via a streamer-data-transmission cable. The illustrated streamers106-111 form a planar horizontal data acquisition surface with respectto the free-surface 112. However, in practice, the data acquisitionsurface may be smoothly varying, for example, due to active sea currentsand weather conditions. In other words, although the streamers 106-111are illustrated in FIGS. 1A and 1B and subsequent figures as straightand substantially parallel to the free-surface 112, in practice, thetowed streamers may undulate as a result of dynamic conditions of thebody of water in which the streamers are submerged. A data acquisitionsurface is not limited to having a planar horizontal orientation withrespect to the free-surface 112. The streamers may be towed at depthsthat angle the data acquisition surface with respect to the free-surface112 or one or more of the streamers may be towed at different depths. Adata acquisition surface is not limited to six streamers as shown inFIG. 1B. In practice, the number of streamers used to form a dataacquisition surface can range from as few as one streamer to as many as20 or more streamers. It should also be noted that the number of sourcesis not limited to a single source. In practice, the number of sourcesselected to generate acoustic energy may range from as few as one sourceto three or more sources and the sources may be towed in groups by oneor more survey vessels.

FIG. 1A includes an xi-plane 114 and FIG. 1B includes an by-plane 116 ofthe same Cartesian coordinate system having three orthogonal, spatialcoordinate axes labeled x, y and z. The coordinate system is used tospecify orientations and coordinate locations within the body of water.The x-direction specifies the position of a point in a directionparallel to the length of the streamers (or a specified portion thereofwhen the length of the streamers are curved) and is referred to as the“in-line” direction. The y-direction specifies the position of a pointin a direction perpendicular to the x-axis and substantially parallel tothe free-surface 112 and is referred to as the “cross-line” direction.The z-direction specifies the position of a point perpendicular to theby-plane (i.e., perpendicular to the free-surface 112) with the positivez-direction pointing downward away from the free-surface 112. Thestreamers 106-111 are generally long cables containing power anddata-transmission lines that connect receivers represented by shadedrectangles 118 spaced-apart along the length of each streamer to seismicdata acquisition system and data-storage devices located on board thesurvey vessel 102.

Streamer depth below the free-surface 112 may be estimated at variouslocations along the streamers using depth measuring devices attached tothe streamers. For example, the depth measuring devices can measurehydrostatic pressure or utilize acoustic distance measurements. Thedepth measuring devices may be integrated with depth controllers, suchas para vanes or water kites that control and maintain the depth andposition of the streamers as the streamers are towed through the body ofwater. The depth measuring devices are typically placed at intervals(e.g., about 300 meter intervals in some implementations) along eachstreamer. Note that in other implementations buoys may be attached tothe streamers and used to help maintain the orientation and depth of thestreamers below the free-surface 112.

FIG. 1A shows a cross-sectional view of the survey vessel 102 towing thesource 104 above a subterranean formation 120. Curve 122 represents atop surface of the subterranean formation 120 located at the bottom ofthe body of water. The subterranean formation 120 is composed of anumber of subterranean layers of sediment and rock. Curves 124, 126, and128 represent interfaces between subterranean layers of differentcompositions. A shaded region 130, bounded at the top by a curve 132 andat the bottom by a curve 134, represents a subterranean hydrocarbondeposit, the depth and positionally coordinates of which may bedetermined, at least in part, by analysis of seismic data collectedduring a marine survey. As the survey vessel 102 moves over thesubterranean formation 120, the source 104 is activated to produce anacoustic signal (often referred to as a “shot”) at spatial and/ortemporal intervals. In other implementations, the source 104 may betowed by one survey vessel and the streamers may be towed by a differentsurvey vessel. The source 104 may be an air gun, marine vibrator, orcomposed of an array of air guns and/or marine vibrators. FIG. 1Aillustrates an acoustic signal expanding outward from the source 104 asa pressure wavefield 136 represented by semicircles of increasing radiuscentered at the source 104. The outwardly expanding wavefronts from thesources may be three-dimensional (e.g., spherical) but are shown invertical plane cross section in FIG. 1A. The outward and downwardexpanding portion of the pressure wavefield 136 is called the “primarywavefield,” which eventually reaches the formation surface 122, at whichpoint the primary wavefield is partially reflected from the formationsurface 122 and partially refracted downward into the subterraneanformation 120, becoming elastic waves within the subterranean formation120. In other words, in the body of water, the acoustic signal iscomposed of compression al pressure waves, or P-waves, while in thesubterranean formation 120, the waves include both P-waves andtransverse waves, or S-waves. Within the subterranean formation 120, atinterfaces between different types of materials or at discontinuities indensity or in one or more of various other physical characteristics orparameters, downward propagating waves may be partially reflected andpartially refracted. As a result, each point of the formation surface122 and each point of the interfaces 124, 126, and 128 may be considereda reflector that becomes a potential secondary point source from whichacoustic and elastic wave energy, respectively, may emanate upwardtoward the receivers 118 in response to the acoustic signal generated bythe source 104. As shown in FIG. 1A, secondary waves of significantamplitude may be generally emitted from points on or close to theformation surface 122, such as point 138, and from points on or veryclose to interfaces in the subterranean formation 120, such as points140 and 142. The upward expanding secondary waves emitted from thesubterranean formation 120 are collectively called the “secondarywavefield.”

The secondary waves that compose the secondary wavefield may begenerally emitted at different times within a range of times followingthe initial acoustic signal. A point on the formation surface 122, suchas the point 138, may receive a pressure disturbance from the primarywavefield more quickly than a point within the subterranean formation120, such as points 140 and 142. Similarly, a point on the formationsurface 122 directly beneath the source 104 may receive the pressuredisturbance sooner than a more distant-lying point on the formationsurface 122. Thus, the times at which secondary and higher-order wavesare emitted from various points within the subterranean formation 120may be related to the distance, in three-dimensional space, of thepoints from the activated source.

Acoustic and elastic waves, however, may travel at different velocitieswithin different materials as well as within the same material underdifferent pressures. Therefore, the travel times of the primarywavefield and secondary wavefield emitted in response to the primarywavefield may be functions of distance from the source 104 as well asthe materials and physical characteristics of the materials throughwhich the wavefields travel. In addition, the secondary expandingwavefronts may be altered as the wavefronts cross interfaces and as thevelocity of sound varies in the media are traversed by the waves. Thesuperposition of waves emitted from within the subterranean formation120 in response to the primary wavefield may be a generally complicatedwavefield that includes information about the shapes, sizes, andmaterial characteristics of the subterranean formation 120, includinginformation about the shapes, sizes, and locations of the variousreflecting features within the subterranean formation 120 of interest toexploration geophysicists.

Each receiver 118 may comprise a pressure sensor that detects variationsin water pressure over time. FIG. 2 shows a side-elevation view of theseismic data acquisition system with a magnified view 202 of thereceiver 118. In this example, the magnified view 202 reveals that thereceiver 118 comprises a pressure sensor 204. The pressure sensors 204may be, for example, hydrophones. Each pressure sensor 204 may measurenon-directional, hydrostatic pressure changes over time and may producespressure wavefield data denoted by p({right arrow over (x)}_(r),t),where {right arrow over (x)}_(r)=(x_(r),y_(r),z_(r)) represent thereceiver Cartesian coordinates, and t represents time. The depth z_(r)of each receiver 118 may be estimated from the depth measurementsobtained from the depth measuring devices located along the streamers.

Seismic data includes data generated by the receivers 118 when detectinghydrostatic pressure changes over time. The streamers 106-111, receivers118, and the survey vessel 102 may include sensing electronics anddata-processing facilities that allow seismic data generated by eachreceiver 118 to be correlated with the time and location of each sourceactivation, absolute positions on the free-surface 112, and absolutethree-dimensional positions with respect to an arbitrarythree-dimensional coordinate system. The seismic data may be stored atthe receivers 118 and/or may be sent along the streamers and datatransmission cables to the survey vessel 102, where the data may bestored electronically or magnetically on data-storage devices locatedonboard the survey vessel 102. The seismic data generated by thereceivers 118 may represent pressure changes in the secondary wavefieldemitted from the subterranean formation 120.

At least a portion of the secondary wavefield emitted from thesubterranean formation 120 may propagate upward toward the free-surface112, forming an up-going wavefield. In FIG. 2, directional arrow 206represents the direction of an up-going wavefield at the location ofreceiver 118, and dashed arrows 210 and 212 represents a down-goingwavefield produced by the up-going wavefield reflection from thefree-surface 112 before reaching the receiver 118. In other words, thepressure wavefield data p({right arrow over (x)}_(r),t) measured by thereceivers 118 is composed of an up-going pressure wavefield componentand a down-going pressure wavefield component. The down-going wavefieldcontaminates seismic data and creates notches in the seismic dataspectral domain.

Each receiver 118 may generate an electrical or optical signal thatencodes the seismic data, which may be recorded on a physicaldata-storage device that may be located at the receiver, at componentsalong the streamer, or onboard the survey vessel. The seismic data isgenerally a time series of consecutively measured values, calledamplitudes, separated in time by a sample rate. The time-series seismicdata measured by a receiver is called a “trace,” which may consist ofthousands of time samples of amplitudes collected at a sample rate ofabout 1 to 5 ms. A trace is generally a record of a subterraneanformation response to acoustic energy that passes from an activatedsource, into the subterranean formation where the reflected acousticenergy is detected by a receiver as described above. A trace generatedby a pressure sensor is pressure wavefield data that may be representedas a set of time-dependent pressure amplitudes denoted by:

p({right arrow over (x)} _(r) ,t)={a _(r)(t _(j))}_(j=1) ^(J)   (1)

-   -   where r is a positive integer trace, receiver, or channel index;        -   j is a time sample index;        -   J is the number of time samples; and        -   a_(r)(t_(j)) is the pressure amplitude of the r-th trace at            time sample t_(j).            Each trace also includes a trace header, not represented in            Equation (1), that identifies the specific receiver that            generated the trace, receiver GPS coordinates, and may            include time sample rate and the number of samples.

As explained above, the secondary wavefield typically arrives first atthe receivers located closest to the sources. The distance from thesources to a receiver is called the “source-receiver offset,” or simply“offset,” which creates a delay in the arrival time of a secondarywavefield from an interface within the subterranean formation. A largeroffset generally results in a longer arrival time delay. Various sets oftraces are collected to form seismic data structures called “gathers”that may be further processed using various seismic data processingtechniques in order to extract information about the structure of thesubterranean formation.

FIG. 3 shows example ray paths that represent an acoustic signal 300that travels from the source 104 into the subterranean formation 120.Dashed-line rays, such as rays 302, represent acoustic energy reflectedfrom the formation surface 122 to the receivers 118 located along thestreamer 108, and solid-line rays, such as rays 304, represent acousticenergy reflected from an interface 124 to the receivers 118 locatedalong the streamer 108. Note that for simplicity of illustration only ahandful of ray paths are represented, and ray paths that extend todeeper interfaces are not shown. Each receiver 118 measures pressurechanges resulting from the acoustic energy reflected from thesubterranean formation 120. The pressure wavefield data generated ateach receiver 118, p({right arrow over (x)}_(r),t), where the receiversubscript r equals 1, 2, 3, 4, and 5, are time recorded as separatetraces in one or more data-storage devices as described above withreference to Equation (1). In the example of FIG. 3, the collection oftraces generated by the five receivers 118 located along the streamer108 for a single activation of the source 104 may be collected to form aseismic data structure called a “common-shot gather.” The tracesgenerated by the receivers 118 located along each of the six streamers108, shown in FIG. 1B, for the same activation of the source 104 may becollected to form six separate common-shot gathers.

FIG. 4 shows a plot of a synthetic common-shot gather composed ofexample traces 401-405 of the pressure wavefield data recorded by thefive receives located along the streamer 108 shown in FIG. 3. Verticalaxis 430 represents time and horizontal axis 432 represents tracenumbers. The traces are arranged so that trace 401 represents theseismic data generated by the receiver 118 located closest to the source104 and trace 405 represents the seismic data generated by the receiver118 located farthest (along the length of the streamer) from the source104. In this example, the traces 401-405 represent variation in theamplitude of the seismic data recorded by the five receivers 118. Theexample traces include wavelets or pulses 406-410 and 411-415represented by peaks colored black that represent the up-going wavefieldmeasured by the pressure sensors 204. The time intervals along thetraces 401-405 from the trace number axis 432 (i.e., time zero) to thewavelets 406-410 represents two-way travel time of the acoustic energyoutput from the source 104 to the formation surface 122 and to thereceivers 118 located along the streamer 108, and the wavelets 411-415represent longer two-way travel time of the acoustic energy output fromthe source 104 to the interface 124 and to the same receivers 118located along the streamer 108. The amplitudes of the peaks or troughsof the wavelets 406-410 and 411-415 indicate the magnitude of thereflected acoustic energy recorded by the receivers 118.

The arrival times of acoustic energy at the receivers increases withincreasing source-receiver offset. The wavelets generated by a formationsurface and an interface reflection of acoustic energy are collectivelycalled a “reflected wave” or simply “reflection” that, in this example,tracks a parabolic-shaped curve. For example, curve 416 represents thedistribution of the wavelets 406-410 reflected from the formationsurface 122, which are called a “formation surface reflected wave”, andcurve 418 represents the distribution of the wavelets 411-415 from theinterface 124, which are called an “interface reflected wave” or“interface reflection.”

FIG. 5 shows an example expanded view of a synthetic gather composed of38 traces. Each trace, such as trace 502, varies in amplitude over timeand represents acoustic energy reflected from the formation surface andfive different interfaces within a subterranean formation as measured bya pressure sensor. In the expanded view, wavelets that correspond toreflection from the same formation surface or interface of thesubterranean formation appear chained together or to overlap. Forexample, wavelets 504 with the shortest transit time represent aformation surface reflection, and wavelets 506 represent an interfacereflected wave emanating from an interface just below the formationsurface. Reflected waves 508-511 represent reflections from interfaceslocated deeper within the subterranean formation.

The synthetic gathers shown in FIGS. 4 and 5 represent ideal cases inwhich acoustic reflections from features of a subterranean formation aremeasured directly by the receivers. But, in practice, seismic datatypically collected in actual marine surveys record other types ofacoustic energy reflections that contaminate the seismic data. Forexample, seismic data obtained from a marine survey records the up-goingwavefield scattered directly from a subterranean formation and thedown-going wavefield reflected from the free-surface described abovewith reference to FIG. 2. The down-going wavefield is essentially atime-delayed up-going wavefield. The down-going wavefield interfereswith the up-going wavefield by cancelling frequencies (i.e., creatingnotches) in the frequency spectrum of the seismic data and creates“ghost” effects in seismic images generated from the seismic data. Theup-going wavefield may be separated from the down-going wavefield whenthe vertical particle velocity wavefield of the acoustic energyreflected from features of the subterranean formation is known. Methodsand systems now described compute an approximate vertical particlevelocity wavefield based on a measured pressure wavefield and the shapeof the free-surface at the time the pressure wavefield is measured. Theapproximate vertical particle velocity wavefield and the measuredpressure wavefield may then be used to compute separate up-going anddown-going wavefields.

FIGS. 6A-6C provide an overview of how a measured pressure wavefield maybe separated into up-going and down-going pressure wavefields without ameasured vertical particle velocity wavefield. In FIG. 6A, syntheticcommon-shot gather 600 represents a portion of a pressure wavefieldmeasured by a number of receivers, such as receivers located along astreamer, after activation of a source. For the sake of simplicity, thegather 600 shows only up-going and down-going pressure wavefieldcomponents of the pressure wavefield. The solid curves represent theup-going pressure wavefield and dashed curves represent the down-goingpressure wavefield. For example, solid curve 606 represents pressurevariations created by a formation surface reflection, and dashed curve608 represents pressure variations created by the same formation surfacereflection with a time delay 610 resulting from the time it takes foracoustic energy to travel up past the streamer to the free-surface andback down to the streamer, as described above with reference to FIG. 2.The methods and systems described herein compute 602 an approximatevertical particle velocity wavefield represented by a gather 604 basedon the pressure wavefield data recorded in the gather 600 and knowledgeof the free-surface shape above the streamers at the time the pressurewavefield is measured. In other words, for each trace in the gather 600that corresponds to the pressure wavefield measured at a receiver, anapproximate vertical particle velocity trace is computed for the samereceiver:

p({right arrow over (x)}_(r),t)→{tilde over (v)}_(z)({right arrow over(x)}_(r),t)   (2)

where {tilde over (v)}_(z)({right arrow over (x)}_(r),t) represents avertical particle velocity trace at the receiver (x_(r),y_(r),z_(r)).

The approximate vertical particle velocity {tilde over (v)}_(z)({rightarrow over (x)}_(r),t) is an approximation of the vertical particlevelocity v_(z)({right arrow over (x)}_(r),t) that may have been obtainedfrom a particle motion sensor collated with the receiver used to measurethe pressure wavefield data p({right arrow over (x)}_(r),t). Theapproximate vertical particle velocity wavefield represented by thegather 604 is similarly composed of up-going and down-going verticalparticle velocity wavefield components identified by solid and dashedcurves, respectively.

Once the approximate vertical particle velocity wavefield is computed,the measured pressure wavefield and the approximate vertical particlevelocity wavefield may be used to compute separate up-going anddown-going pressure wavefield components of the measured pressurewavefield. In FIG. 6B, the pressure wavefield, denoted by p, istransformed 612 from the space-time (“s-t”) domain using a fast Fouriertransform (“FFT”), or a discrete Fourier transform (“DFT”), to obtainpressure wavefield P in the frequency-wavenumber (“f-k”) domain. In thefrequency-wavenumber domain, the pressure wafefield P may be decomposedinto a sum of the up-going pressure wavefield and the down-goingpressure wavefield as follows:

P=P ^(up) =P ^(down)   (3)

where

-   -   P^(up) represents the up-going pressure wavefield in thef-k        domain; and    -   P^(down) represents the down-going pressure wavefield in the f-k        domain.        The approximate vertical particle velocity wavefield, denoted by        {tilde over (v)}_(z), is also transformed 614 from the s-t        domain using an FFT, or a DFT, to obtain an approximate vertical        particle velocity wavefield {tilde over (V)}_(z) in the f-k        domain. The up-going and down-going pressure wavefields in the        f-k domain are computed 616 according to

$\begin{matrix}{P^{up} \approx {\frac{1}{2}\left\lbrack {P - {\frac{\rho\omega}{k_{z}}{\overset{\sim}{V}}_{z}}} \right\rbrack}} & \left( {4a} \right) \\{P^{down} \approx {\frac{1}{2}\left\lbrack {P + {\frac{\rho\omega}{k_{z}}{\overset{\sim}{V}}_{z}}} \right\rbrack}} & \left( {4b} \right)\end{matrix}$

where

-   -   ρ is the density of water;    -   ω is angular frequency; and    -   k_(z) is the z-direction or vertical wavenumber.        In other words, once the approximate vertical particle velocity        wavefield {tilde over (V)}_(z) is computed, the pressure        wavefield P may be separated, or decomposed, into up-going and        down-going pressure wavefields according to Equations (4a) and        (4b). The separate up-going and down-going pressure wavefields,        P^(up) and P^(down), may be transformed 618 and 620 from the f-k        domain back to the s-t domain using an inverse FFT (“IFFT”), or        inverse (“IDFT”), to obtain separate up-going and down-going        pressure wavefields, p^(up) and p^(down), in the s-t domain.        Alternatively, the measured pressure wavefield and the        approximate vertical particle velocity wavefield may be used to        compute approximate up-going and down-going vertical particle        velocity wavefield components of the vertical particle velocity        wavefield.

In FIG. 6C, the up-going and down-going pressure wavefields combined inthe pressure wavefield represented by the gather 600 of FIG. 6A areshown in separate up-going pressure wavefield gather 622 and down-goingpressure wavefield gather 624. The pressure wavefield represented by theup-going pressure wavefield in the gather 622 may be subjected tofurther seismic data processing to remove noise and other effects andserve as input to imaging methods that generate seismic images of thesubterranean formation. The resulting seismic images may havesignificantly higher resolution and deeper signal penetration into thesubterranean formation than seismic images computed with the unseparatedseismic data represented in the gather 600.

Methods and systems compute an approximate vertical particle velocitywavefield based on the measured pressure wavefield and on knowledge ofthe shape of the free-surface above the data acquisition surface whenthe pressure wavefield is measured. Methods and systems described hereincompute the shape of the free-surface above the data acquisition surfacebased on the measured pressure wavefield. FIGS. 7-15 illustratecalculation of the shape of a free-surface above a streamer based on apressure wavefield measured by receivers located in the streamer. Theshape of the free-surface at the time the pressure wavefield is measuredis assumed to be in a fixed or frozen-in-time state called a frozenfree-surface.

FIG. 7 shows a side-elevation view of a streamer 702 located in a bodyof water below a free-surface 704. In FIG. 7, horizontal axis 706represents the in-line, or x-direction, vertical axis 708 representsdepth, and circle 710 represents the cross-line or, y-direction,orthogonal to the xi-plane. The depth z_(r) and the elevation of thefree-surface are estimated with respect to the geoid, which correspondsto the x-axis 706. The geoid is the hypothetical surface of the earththat coincides with the mean sea level and is used to define zeroelevation (i.e., z=0). The streamer 702 includes 14 spaced apartreceivers, such as receiver 712, that each measure a different portionof a pressure wavefield. The streamer 702 may be part of larger dataacquisition surface composed of any number of streamers towed by asurvey vessel not shown. Each receiver may generate pressure wavefielddata p({right arrow over (x)}_(r),t) as described with reference toEquation (1), such as pressure wavefield data p({right arrow over(x)}_(s),t) generated for the fifth receiver 712 of the streamer 702.

FIGS. 7-9 and 16 included the frozen free-surface 704 which represents asnapshot of the free-surface above the streamer 702 when the pressurewavefield data p({right arrow over (x)}_(r),t) is recorded. The frozenfree-surface 704 has a fixed cross-sectional shape above the streamer702 when the pressure wavefield data p({right arrow over (x)}_(r),t) isgenerated for each activation of a source, consequently referred to as a“frozen free-surface.” In practice, the actual shape of the frozenfree-surface 704 is not known but the frozen free-surface 704 isincluded in the follow illustrations in order to depict computation ofan approximate frozen free-surface as now described with reference toFIGS. 8-16.

The fixed cross-sectional shape of the frozen free-surface 704 iscomputed by forward and backward extrapolation of the pressure wavefieldat a series of trial depths above the streamer. FIG. 8 shows thestreamer 702 and frozen free-surface 704′ and an example series of trialdepths Z₁ through Z_(N), where N is a positive integer. Dots, such asdot 802, identify the series of regularly spaced trial depths above thereceiver 712. In this example, the trial depths extend beyond the frozenfree-surface 704 as represented by fmal trial depth 804 Z_(N).

Extrapolation is carried out by first transforming the pressurewavefield data generated by each receiver from the s-t domain to the f-kdomain as follows:

p({right arrow over (x)}_(r),t)→P(k_(x),k_(y),ω|z_(r))   (5)

The transformation may be executed with an FFT or a DFT. Next, at eachtrial depth, the pressure wavefield data generated at each receiver isforward and backward extrapolated to the trial depth level to obtainforward and backward extrapolated wavefields that correspond to thetrial depth. For each receiver, the pressure wavefield data is forwardextrapolated to a trial depth Z_(n) according to

P ^(F)(k _(x) ,k _(y) ,ω|Z _(n))=P(k _(x) ,k _(y) ,ω|z _(r))e ^(−ik)^(z) ^((z) ^(r) ^(−z) ^(n) ⁾   (6)

and backward extrapolated to the same trial depth Z_(n) according to

P ^(B)(k _(x) ,k _(y) ,ω|Z _(n))=P(k _(x) ,k _(y) ,ω|z _(r))e ^(ik) ^(z)^((z) ^(r) ^(−z) ^(n) ⁾   (7)

where

-   -   i is the imaginary unit √{square root over (−1)};    -   k_(x) is the horizontal wavenumber in the x-direction;    -   k_(y) is the horizontal wavenumber in the y-direction; and    -   k_(z)=√{square root over (k²−k_(x) ²−k_(y) ²)}.        For each trial depth Z_(n), the forward and backward        extrapolated pressure wavefield data associated with each        receiver is then transformed from thef-k domain back to the s-t        domain:

P^(F)(k_(x),k_(x),ω|Z_(n))→p^(F)(x_(r),y_(r),t|Z_(n))   (8a)

P^(B)(k_(x),k_(y),ω|Z_(n))→p^(B)(x^(r),y_(r),t|Z_(n))   (8b)

where

-   -   superscript “F” represents forward extrapolated; and    -   superscript “B” represents backward extrapolated.        The transformation may be executed with an IFFT or an IDFT.

FIG. 9 shows an example of forward and backward extrapolated pressurewavefield data at the trial depth Z_(n) 902 for the fifth receiver 712.The forward and backward extrapolated pressure wavefield data at thetrial depth Z_(n) are represented by p^(F)(x₅,y₅,t|Z_(n)) andp^(B)(x₅,y₅,t|Z₇), respectively. For each trial depth Z_(n) with n=1, .. . , N, forward and backward extrapolated pressure wavefield datap^(F)(x_(r),y_(r),t|Z_(n)) and p^(B)(x_(r),y_(r),t|Z_(n)) are computedfor each receiver (i.e., r=1, . . . , 14) of the streamer 702.

For each trial depth Z_(n), the forward extrapolated pressure wavefielddata computed for each receiver are collected to form a forwardextrapolated gather

p ^(F)(x,y,t|Z _(n))={p ^(F)(x _(r) ,y _(r) ,t|Z _(n))}_(r=1) ^(R)  (9a)

where R is the number of receivers.

Backward extrapolated pressure wavefield data computed for each receiverare also collected to form a backward extrapolated gather

p ^(B)(x,y,t|Z _(n))={p ^(B)(x _(r) ,y _(r) ,t|Z _(n))}_(r=1) ^(R)  (9b)

FIG. 10 shows a series of forward extrapolated gathers and correspondingbackward extrapolated gathers computed for each trial depth Z_(n) withn=1, . . . , N. Rectangle 1002 represents a common-shot gather ofpressure wavefield data p generated by a number of receivers locatedalong a streamer. Pair of rectangles represent the forward and backwardextrapolated gathers computed for each of the trial depths Z_(n). Forexample, pair of rectangles 1004 and 1006 represent forward and backwardextrapolated gathers for the first trial depth Z₁and pair of rectangles1008 and 1010 represent forward and backward extrapolated gathers forthe final trial depth Z_(N).

A difference gather may be computed for each pair of forward andbackward extrapolated gathers. In other words, for each trial depthZ_(n), a difference gather is computed as follows:

d(x,y,t|Z _(n))=p ^(F)(x,y,t|Z _(n))−p ^(B)(x,y,t|Z _(z))   (10)

Amplitudes of the forward extrapolated gather p^(F)(x,y,t|Z_(n)) arerepresented by a_(r) ^(F)(t_(j)|Z_(n)) and amplitudes of the backwardextrapolated gather p^(B)(x,y,t|Z_(n)) are represented by a_(r)^(B)(t_(j) 51 Z_(n)), where r is a trace index, t_(j) is the time sampleindex, and Z_(n) identifies the trial depth. Amplitude differences,A_(r)(t_(j)|Z_(n)), for each difference gather d(x,y,t|Z_(n)) may beexecuted according to the following pseudo code:

1 for n = 1,...,N { //trial depth 2 for r = 1,...,R { //receivers/traces3 for j = 1,...,J { //time samples 4 A_(r)(t_(j)|Z_(n)) = a_(r)^(F)(t_(j)|Z_(n)) − a_(r) ^(B)(t_(j)|Z_(n)); 5 } 6 } 7 store differencegather d(x,y,t|Z_(n)) = {{A_(r)(t_(j)|Z_(n))}_(j=1) ^(J)}_(r=1)^(R);//gather 8 }

FIG. 11 shows difference gathers computed from the pairs of forward andbackward extrapolated gathers shown in FIG. 10. Rectangle 1102represents a difference gather obtained by computing the differencebetween the pair of forward and backward extrapolated gathers 1004 and1006 shown in FIG. 10. Rectangle 1104 represents a difference gatherobtained by computing the difference between the pair of forward andbackward extrapolated gathers 1008 and 1010 shown in FIG. 10.

A series of time windows are applied to each difference gather and amaximum energy difference is calculated for each time window. FIGS.12A-12C show an example calculation of a maximum energy difference foreach time window. FIG. 12A shows an example of a series of time windowsapplied to a time region 1200 of a difference gather d(x,y,t|Z_(n))1202. In this example, the time windows are represented by rectanglesthat span a time subinterval and the full set of traces of thedifference gather 1202. The time windows are denoted by W_(m), wherem=1, . . . , M is the time window index and M is the total number oftime windows in the time window series. Initially, time window W₁ islocated over the earliest time interval of the difference gather 1202,time window W_(m) is located over an intermediate time interval, andtime window W_(M) is located over a later time interval. In certainimplementations the time windows may intersect while in otherimplementations the time windows may not intersect. In alternativeimplementations, the time windows and the region of the differencegather the series of time windows are applied to may be hyperbolic inorder to approximate the curved shaped of reflections created by sourcereceiver offset in common-shot gathers described above with reference toFIG. 4. In still other implementations, the time series windows may beapplied to the full difference gather.

FIG. 12B shows a rectangle 1204 that represents an enlargement of thetime window W_(m) located over a time interval of the difference gather1202 shown in FIG. 12. Solid circles located within the time windowW_(m) represent amplitude differences A_(r)(t_(j)|Z_(n)) calculatedaccording to Equation (10). For example, solid circle 1206 represents anamplitude difference A₉(t_(j)|Z_(n)) calculated for a trace r=9. Foreach amplitude difference in the time window W_(m), a correspondingenergy difference is calculated according to

E(x _(r) ,y _(r) ,t _(j) ∈W _(m) |Z _(n))=[A _(r)(t _(j) |Z _(n))]²  (11)

Rectangle 1208 represents the time window W_(m) with energy differencescalculated according to Equation (11) for each of the amplitudedifferences in the time window W_(m). For example, E(x₉,y₉,t_(j)|Z_(n))represents the energy difference for the 9-th trace at the j-th timesample determined by computing the square of the amplitude differenceA₉(t_(j)|Z_(n)) represented by circle 1206 in rectangle 1204. A maximumenergy difference is determined for each trace with time samples in therectangle 1208 according to:

$\begin{matrix}{{E_{\max}\left( {x_{r},y_{r},{W_{m}Z_{n}}} \right)} = {\max\limits_{t}\left\{ {E\left( {x_{r},y_{r},{{t_{j} \in W_{m}}Z_{n}}} \right)} \right\}}} & \left( {12a} \right)\end{matrix}$

The quantity E_(max)(x_(r), y_(r), W_(m)|Z_(n) represents the maximumenergy difference for the r-th trace in the time window 1208. In FIG.12B, open circles identify the maximum energy difference in each trace.For example, open circle 1210 identifies the maximum energy differenceE_(max)(x₉,y₉,W_(m)|Z_(n) of the seven energy differences located alongthe 9-th trace with time samples in the time window 1208. The maximumenergy differences in the time window W_(m) are collected to form avector of maximum energy-differences given by:

{right arrow over (E)} _(max)(W _(m) |Z _(n))=[E _(max)(x ₁ ,y ₁ ,W _(m)|Z _(n)) . . . E _(max)(x _(R) ,y _(R) ,W _(m) |Z _(n))]^(T)   (12b)

For example, in FIG. 12B, vector 1212 represents the vector of maximumenergy-differences for the time window 1208.

FIG. 12C shows the time windows shown in FIG. 12A with correspondingvectors of maximum energy differences computed for each time window. Forexample, time window W₁ has associated vector of maximum energydifferences, {right arrow over (E)}_(max)(W₁|Z_(n)), and time window W₂has associated vector of maximum energy differences, {right arrow over(E)}_(max)(W₂|Z_(n)).

Next, for each time window applied to the N difference gathers, a peakenergy is computed from the N vectors of maximum energy differencescalculated for the time window. FIG. 13 shows the M time windows appliedto the N difference gathers, each of which is identified by a trialdepth Z_(n). For example, time window W_(m) is applied to each of the Ndifference gathers over the same time interval and a vector of maximumenergy difference {right arrow over (E)}_(max)(W_(m)|Z_(n)) is computedfor each of the N difference gathers. The maximum energy differences ofthe vectors of maximum energy differences formed for the time windowW_(m) applied to each of the N difference gathers are collected to forma set of maximum energy differences {E_(max)(x_(r),y_(r),W_(m)|Z_(n))}for r=1, . . . , R and n=1, . . . , N. For each time window W_(m), apeak energy is then identified from the set of maximum energydifferences

$\begin{matrix}{{E_{peak}\left( {x_{r},y_{r},z_{{peak},\; r}} \right)} = {\max\limits_{n}\left\{ {E_{\max}\left( {x_{r},y_{r},{W_{m}Z_{n}}} \right)} \right\}}} & (13)\end{matrix}$

where z_(peak,r) equals the trial depth Z_(n) of the maximum energydifference in the set {E_(max)(x_(r),y_(r),W_(m)|Z_(n))}.

Each maximum energy difference E_(max) (x_(r),y_(r),W_(m)|Z_(n)) in theset {E_(max)(x_(r),y_(r),W_(m)|Z_(n))} corresponds to a receiver asdescribed above with reference to FIG. 12B. As a result, receivercoordinates (x_(r),y_(r)) associated with the peak energyE_(peak)(x_(r),y_(r),z_(peak,r)) are the receiver coordinates associatedwith z_(peak,r), which includes the subscript r to identify thereceiver. The peaks z_(peak,r) and associated receiver coordinates(x_(r),y_(r)) are collected to form a set of points{(x_(r),y_(r),z_(peak,r))} that approximate the shape of the frozenfree-surface above the streamer.

FIG. 14 shows a side-elevation view of the streamer 702 and frozenfree-surface 704 described above with reference to FIG. 7. Open circleslocated along the frozen free-surface 704′ above the receivers representpoints in the set {(x_(r),y_(r),z_(peak,r))}. For example, open circle1402 represent a point (x₅,y₅,z_(peak,5)) along the frozen free-surface704′ above the fifth receiver 712 with receiver coordinates (x₅,y₅,z₅).

Implementations are not limited to generating a difference gather asdescribed above with reference to FIG. 11. In alternativeimplementations, two separate time windows may be applied to the sametime intervals of corresponding forward and backward extrapolatedgathers and calculation of amplitude differences is limited to theamplitudes within the two time windows.

FIG. 15 shows an example calculation of amplitude differences for twoseparate time windows 1502 and 1504 applied to the same time intervalsof forward and backward extrapolated gathers 1506 and 1508. In thisexample, the forward and backward extrapolated gathers 1506 and 1508represent the extrapolated gathers used to compute the difference gather1202 described above with reference to FIGS. 12A-12C. Instead ofcomputing the entire difference gather 1202, a time window 1510containing amplitude differences, a_(r) ^(F)(t_(j)|Z_(n))−a_(r)^(B)(t_(j)|Z_(n), of corresponding amplitudes in the two time windows1502 and 1504 is computed for every time sample in the time window 1510.The amplitude differences in the time window 1510 correspond to theamplitude differences in the time window 1204 in FIG. 12B. The energydifferences are computed for corresponding amplitude differences in thetime windows 1502 and 1504 as follows:

E(x _(r) ,y _(r) ,t _(j) ∈W _(m) |Z _(n))=[a _(r) ^(F)(t _(j) |Z _(n))−a_(r) ^(B)(t _(j) |Z _(n))]²   (14)

The energy differences computed from the amplitude differences in thetime window 1510 correspond to the energy differences in the time window1208 shown in FIG. 12B and a maximum energy difference is determined foreach trace as described above with reference to Equation (12b). Next,for each time window applied to the N corresponding forward and backwardextrapolated gathers, a peak energy is computed as described above withreference to Equation (13) to obtain a set of points{(x_(r),y_(r),z_(peak,r))} that approximate the shape of the frozenfree-surface above the streamer.

The shape of the frozen free-surface above the streamer may beapproximated by applying interpolation to the set of points{(x_(r),y_(r),z_(peak,r))}. For example, polynomial interpolation,spline interpolation, and Gaussian interpolation may be used to computean approximate frozen free-surface profile above the streamer based onthe set of points {(x_(r),y_(r),z_(peak,r))}.

FIG. 16A shows a side-elevation view of the streamer 702 and frozenfree-surface 704 and open circles that represent the set of points[(x_(r),y_(r),z_(peak,r))]. Dashed curve 1602 represents an approximatefrozen free-surface profile, f_(int)(x), of the frozen free-surface 704above the streamer 702 between the first receiver coordinate x₁ and thelast receiver coordinate x_(l) identified by dashed lines 1606 and 1608,respectively. Note that the cross-line receiver coordinate y_(r) issuppressed, because the approximate frozen free-surface profile isdetermined in the in-line direction. FIG. 16A also shows a source 1604(represented by a shaded circle) towed by a survey vessel (not shown).But the approximate frozen free-surface profile 1602 does notapproximate the frozen free-surface above the source 1604. Theapproximate frozen free-surface profile may be extended to approximatethe frozen free-surface above the source 1604 by computing a frozenfree-surface extension.

FIG. 16B shows a plot of an extended portion of the approximate frozenfree-surface profile. Dotted curve 1610 represents an approximate frozenfree-surface extension above the source 1604. The frozen free-surfaceextension 1610 may be calculated from a free-surface model based onparameters associated with the weather conditions measured at the timeof the marine survey. For example, a Pierson-Moskowitz model of thefree-surface may be used to calculate the frozen free-surface extension1610. The Pierson-Moskowitz model of a free-surface is based on the windblowing steadily for a long period of time over a large free-surfacearea to produce waves that eventually reach a state of equilibrium. Thiscondition is referred to as a “fully developed sea.” ThePierson-Moskowitz model used to calculate an extension to theapproximate frozen free-surface profile at a point x in the x-directionis given by:

$\begin{matrix}{{f_{ext}(x)} = {\frac{1}{L}{\sum\limits_{q = 0}^{Q - 1}\; {{F\left( K_{q} \right)}^{\; K_{q}x}}}}} & (15)\end{matrix}$

where for the integer index q≧0,

$\begin{matrix}{\; {{F\left( K_{q} \right)} = {\sqrt{2\pi \; {{LW}\left( K_{q} \right)}}\left\{ {{{\begin{matrix}{\left\lbrack {{N\left( {0,1} \right)} + {j\; {N\left( {0,1} \right)}}} \right\rbrack \text{/}\sqrt{2}} & {{{{for}\mspace{14mu} i} \neq 0},{Q\text{/}2}} \\{N\left( {0,1} \right)} & {{{{for}\mspace{14mu} i} = 0},{Q\text{/}2}}\end{matrix}\mspace{79mu} {and}\mspace{14mu} {for}\mspace{14mu} q} < 0},{{F\left( K_{q} \right)} = {{F\left( K_{- q} \right)}^{*}.}}} \right.}}} & (16)\end{matrix}$

The parameter W(K_(q)) is the Pierson-Moskowitz spatial roughnessspectrum, which for a fully developed sea surface in one-dimension(e.g., x-direction) is given by:

$\begin{matrix}{{W\left( K_{q} \right)} = {\left\lbrack \frac{\alpha}{4{K_{q}}^{3}} \right\rbrack {\exp \left( {{- \beta}\; g^{2}\text{/}K_{q}^{2}U_{w}^{4}} \right)}}} & (17)\end{matrix}$

where

-   -   K_(q) is the spatial wavenumber;    -   U_(w) is the wind speed measured at a height of about 19 meters;    -   α is 8.0×10⁻³;    -   β is 0.74; and        -   g is the acceleration due to gravity.            In Equations (15) and (16), the spatial wavenumber for            component q is given by K_(q)=2πq/L, where L is the length            of free-surface. The random number N(0,1) may be generated            from a Gaussian distribution having zero mean and a unit            variance. As a result, the free-surface is formed by adding            each wavenumber component imposing random phase shifts. A            frozen in time Pierson-Moskowitz free-surface may be            computed from Equation (15) using a FFT for computational            efficiency.

The frozen free-surface extension f_(ext)(x) may be combined with theapproximate frozen free-surface profile f_(int)(x) to represent thefrozen free-surface above the source and receivers by

$\begin{matrix}{{f(x)} = \left\{ \begin{matrix}{f_{ext}(x)} & {{{for}\mspace{14mu} x_{0}} \leq x < x_{1}} \\{f_{int}(x)} & {{{for}\mspace{14mu} x_{1}} \leq x \leq x_{l}}\end{matrix} \right.} & (18)\end{matrix}$

When extending the approximate frozen free-surface profile toapproximate the frozen free-surface above the source 1604, theapproximate frozen free-surface profile f(x) reduces to f_(int)(x).

In alternative implementations, the approximate frozen free-surfaceextension may be expanded to include a time parameter that characterizesthe frozen free-surface at different times. Free-surface waves aregenerally dispersive and in deep water, and the frequency and wavenumberare related by a dispersion relation given by:

Ω(K _(q))=√{square root over (gK _(q))}  (19)

Equation (19) implies that each spatial harmonic component of thefree-surface wavefield may move with a definite phase velocity. As aresult, in general, free-surface waves of longer wavelengths travelfaster relative to waves with shorter wavelengths. Combining Equations(15) and (19) gives a time-varying frozen free-surface:

$\begin{matrix}{{f_{ext}\left( {x,t} \right)} = {\frac{1}{L}{\sum\limits_{q = 0}^{Q - 1}\; {{F\left( K_{q} \right)}^{\; {({{K_{q}x} - {{\Omega {(K_{q})}}\; t}})}}}}}} & (20)\end{matrix}$

where t is instantaneous time. Equation (20) characterizes aone-dimensional rough free-surface moving in the positive x-directionand may be used to compute the frozen free-surface extension 1610 atearlier or later times.

Consider a free-surface shape at an instant in time t with wave heightsgiven by Equation (20). The wavenumber spectrum F(K_(q)) of thefree-surface is computed according to Equation (16) and an arbitraryknown dispersion relation Ω(K_(q)) is calculated according to Equation(19) may be used to calculate the frozen free-surface at an earlier(t−Δt) or a later (t+Δt) time by:

$\begin{matrix}{{f_{ext}\left( {x,t} \right)} = {\frac{1}{L}{\sum\limits_{q = 0}^{Q - 1}\; {{F\left( K_{q} \right)}^{{({{K_{q}x} - {{\Omega {(K_{q})}}\Delta \; t}})}}}}}} & (21)\end{matrix}$

The frozen free-surface wavefield reflectivity (i.e., the response of aunit point source at the receiver position {right arrow over (r)}_(r))may be computed for a source at a location {right arrow over(x)}_(s)=(x_(s),y_(s),z_(s)) and a receiver at a location {right arrowover (x)}_(r)=(x_(r),y_(r),z_(r)) using:

$\begin{matrix}{{R\left( {{\overset{\rightharpoonup}{x}}_{r}{\overset{\rightharpoonup}{x}}_{s}} \right)} = {{\frac{1}{4j}{H_{0}^{(1)}\left( {k{{\overset{\rightharpoonup}{x}}_{d}}} \right)}} + {\frac{k}{8}{\int_{S_{r}}^{\;}{{H_{0}^{(1)}\left( {k{{{\overset{\rightharpoonup}{x}}_{0} - {\overset{\rightharpoonup}{x}}_{r}}}} \right)}{H_{1}^{(1)}\left( {k{\overset{\rightharpoonup}{\rho}}} \right)}{\eta \left( x^{\prime} \right)}\ {x^{\prime}}}}}}} & (22) \\{\mspace{79mu} {with}} & \; \\{\mspace{79mu} {{\eta \left( x^{\prime} \right)} = {\frac{{{- \left( {x^{\prime} - x_{s}} \right)}\frac{{f(x)}}{x}}_{x = x^{\prime}}}{\overset{\rightharpoonup}{\rho}} + \frac{\left\lbrack {{f\left( x^{\prime} \right)} - z_{s}} \right\rbrack}{\overset{\rightharpoonup}{\rho}}}}} & \;\end{matrix}$

where

${H_{n}^{(1)}(x)} \cong {\sqrt{\frac{2}{\pi \; x}}{\exp \left( {\left( {x - \frac{\pi}{4} - \frac{n\; \pi}{2}} \right)} \right)}}$

is the asymptotic form of the first-order Hankel function with n=0and 1. The parameters of Equation (22) are represented in FIG. 17 asfollows:

k is the wavenumber of the propagating wavefield;

f(x) is the approximate frozen free-surface profile represented bydashed curve 1702;

[x₀,f(x₀)] is a coordinate position 1704 of a running scattering pointon the approximate frozen free-surface profile;

{right arrow over (x)}₀ is a vector 1706 from the origin of theCartesian coordinate system to the running scattering point 1704;

{right arrow over (r)}_(r) is a vector 1708 from the origin to areceiver 1710;

{right arrow over (x)}₀−{right arrow over (x)}_(r) is a vector 1712 fromthe running scattering point 1704 to the receiver 1710;

{right arrow over (x)}_(d) is a vector 1714 from the origin to a source1716;

{right arrow over (x)}_(d) is a vector 1718 from the source 1716 to thereceiver 1710;

{right arrow over (ρ)} is a vector 1720 from the source 1716 to thescattering point 1704;

S_(r) is the path of the streamer which may be interpolated from thedepth measurements obtained from the depth measuring devices locationalong the streamer; and

η(x′)={circumflex over (n)}·{circumflex over (ρ)}=cos θ is the obliquityfactor with normal vectors {circumflex over (n)} 1722 and {circumflexover (ρ)} 1724 corresponding to the frozen free-surface normal and theunit vector direction of the incident field at [x₀,f(x₀)] 1704 and θ isthe angle between the vectors {circumflex over (n)} 1722 and {circumflexover (ρ)} 1724.

Next, the gradient of the pressure wavefield in the frequency domain,denoted by ∇_(r)P, may be computed. Computation of the gradient ∇_(r)Pgenerally depends on the depth of the source in relation to the depth ofthe streamer. FIG. 18A shows an example side-elevation view of thesource 1604 located shallower than the streamer 702, and FIG. 18B showsan example side-elevation view of the source 1604 located deeper thanthe streamer 702. In FIGS. 18A-18B, vectors, such as vector {right arrowover (x)} 1802, represent coordinates (x,y,z). Subscript-r vectors, suchas vector {right arrow over (r)}^(r) 1804, represent receivercoordinates (x_(r),y_(r),z_(r)), and subscript-s vectors, such as vector{right arrow over (r)}_(s) in FIG. 18A and vector {right arrow over(x)}_(s) 1808 in FIG. 18B represent source coordinates(x_(s),y_(s),z_(s)). When the depth of the source 1604 is less than thedepth of the streamer, as shown in FIG. 18A, the gradient of thepressure wavefield may be calculate by solving the following integralequation for ∇_(r)P({right arrow over (x)}_(r),ω) in the frequencydomain:

∫_(S) _(r) dS _(r) {right arrow over (n)}·R({right arrow over (x)} _(r),{right arrow over (x)})∇_(r) P({right arrow over (r)}_(r),ω)=a(ω)R({right arrow over (x)} _(s) ,{right arrow over (x)})+∫_(S)_(r) dS _(r) {right arrow over (n)}·P({right arrow over (x)}_(r),ω)∇_(r) R({right arrow over (x)}r ,{right arrow over (x)})   (23)

where

a(ω) is the Fourier transform of the source-time function for the sourceat the coordinate location {right arrow over (x)}_(s);

P({right arrow over (x)}_(r),ω) is the pressure wavefield data in thefrequency domain obtained from transforming the pressure wavefield datap({right arrow over (x)}_(r),t) using an FFT or a DFT.

R({right arrow over (x)},{right arrow over (x)}_(s)) is the frozenfree-surface reflectivity calculated according to Equation (22);

∇_(r)R({right arrow over (x)}_(r),{right arrow over (x)}) is the radientof the reflectivity; and ∇_(r)R({right arrow over (x)}_(r),ω) is thegradient of the pressure wavefield at the receiver.

Equation (23) is a Fredholm integral equation of the first kind for thegradient of the pressure wavefield ∇_(r)P({right arrow over (x)}_(r),ω)where the right-hand side of Equation (23) contains only knownparameters such as the pressure wavefield P({right arrow over(x)}_(r),ω) and the free-surface wavefield reflectivity R({right arrowover (x)}_(r),{right arrow over (x)}). The gradient of the reflectivity,∇_(r)R( {right arrow over (x)}_(r),{right arrow over (x)}), may becomputed using numerical gradient techniques applied to the free-surfacewavefield reflectivity R({right arrow over (x)}_(r),{right arrow over(x)}) in Equation (22). On the other hand, when the source is located ata depth below the streamer S_(r), as shown in FIG. 18B, the expressionused to calculate the gradient of the pressure wavefield ∇_(r)P({rightarrow over (w)}_(r),ω) over the frequency range is give by:

∫_(S) _(r) dS _(r) {right arrow over (n)}·R({right arrow over (r)},{right arrow over (x)})∇_(r) P({right arrow over (x)} _(r),ω)=∫_(S)_(r) {right arrow over (n)}·P({right arrow over (x)} _(r),ω)∇_(r)R({right arrow over (x)} _(r) ,{right arrow over (x)})   (24)

In Equation (24), the source function a(ω) is zero. Note that thesolutions of Equations (23) and (24) become unstable when the spectrumof the pressure wavefield has very small values (e.g., close to receiverghost notches).

Depending on whether the source is at a depth above or below thestreamer, as shown in FIGS. 18A and 18B, respectively, Equations (23)and (24) may be solved numerically for the gradient of the pressurewavefield, ∇_(r)P({right arrow over (x)}_(r),ω) at receiver locationsalong the streamer using quadrature or expansion methods. For quadraturemethods, the integrals may be approximated by quadrature formulas andthe resulting system of algebraic equations is solved. For expansionmethods, the solution may be approximated by an expansion in terms ofbasis functions.

An approximate normal particle velocity at each receiver location alongthe streamer may be calculated according to:

$\begin{matrix}{{{\overset{\sim}{V}}_{n}\left( {{\overset{\rightharpoonup}{x}}_{r},\omega} \right)} = {{- \frac{i}{\rho\omega}}{\overset{\rightharpoonup}{n} \cdot \bigtriangledown_{r}}{P\left( {{\overset{\rightharpoonup}{x}}_{r},\omega} \right)}}} & (25)\end{matrix}$

where

{right arrow over (n)} is a normal vector at a receiver; and

{right arrow over (n)}·∇_(r)P({right arrow over (x)}_(r),ω) is thenormal derivative of the pressure wavefield P at the receiver.

FIG. 19 shows a segment of a streamer 1902 located beneath anapproximate frozen free-surface profile 1904 in the xz-plane. A normalvector 1906 to the streamer 1902 at the receiver 1908 is given by:

$\begin{matrix}{\overset{\rightharpoonup}{n} = {\left( {n_{x},n_{z}} \right) = {\left( {{{- \sin}\mspace{11mu} \varphi},{\cos \mspace{11mu} \varphi}} \right) = \left( {{- \frac{z_{r}}{x}},\frac{x_{r}}{q}} \right)}}} & (26)\end{matrix}$

The resulting approximate vertical particle velocity for each receiveris given by:

{tilde over (V)} _(z)({right arrow over (x)} _(r),ω)=cos φ·{tilde over(V)} _({right arrow over (n)})({right arrow over (x)} _(r),ω)   (27)

The approximate vertical particle velocity {tilde over (V)}_(z)({rightarrow over (x)}_(r),ω) may be transformed from the space-frequencydomain to the f-k domain using an FFT or DFT to obtain {tilde over(V)}_(z)({right arrow over (k)},ω), where {right arrow over (k)} is thewavevector (i.e., {right arrow over (k)}=(k_(x),k_(y),k_(z))), which maybe used to compute separate approximate up-going and down-going pressurewavefields according to Equations (4a) and (4b).

FIG. 20 shows a flow-control diagram of a method that computes separatedwavefields from measured pressure wavefields. In block 2001, a gather ofpressure wavefield data is received. The gather may be a common-shotgather of pressure wavefield data obtained from receivers located alonga streamer of a data acquisition surface, as described above withreference to FIG. 3. In block 2002, the gather may be transformed fromthe s-t domain to the f-k domain as described above with reference toEquation (5). A for-loop beginning with block 2003 repeats thecomputational operations of blocks 2004-2014 for N trial depths. Inblock 2004, a forward extrapolated wavefield computed for a trial depthz_(n), as described above with reference to Equation (6). In block 2005,the forward extrapolated wavefield is transformed from f-k domain backto the s-t domain as described above with reference to Equation (8a)using an FFT or a DFT to obtain a forward extrapolated wavefield in thes-t domain. In block 2006, a backward extrapolated wavefield computedfor a trial depth z_(n,) as described above with reference to Equation(6). In block 2007, the backward extrapolated wavefield is transformedfrom f-k domain back to the s-t domain as described above with referenceto Equation (8a) using an FFT or a DFT to obtain a backward extrapolatedwavefield in the s-t domain. In block 2008, a difference gather iscomputed from the forward and back extrapolated wavefields as describedabove with reference to Equation (10) and with reference to FIG. 11. Afor-loop beginning with block 2009 repeats the computational operationsof blocks 2010-2012 for a series of time windows as described above withreference to FIGS. 12A-12C. In block 2010, a routine “compute maximumenergy difference” is called as described below with reference to FIG.21. In decision block 2011, when window index m equals the number M ofwindows in the time window series, control flows to decision block 2012.Otherwise, control flows to block 2012 and the window index isincremented and the operation represented by block 2010 is repeated. Indecision block 2013, when trial depth index n equals the number N oftrial depth in the series of trial depths, control flows to block 2015.Otherwise, the method increments the trial depth index n in block 2014and repeats the operations represented by blocks 2004-2012. In block2015, a routine “wavefield separation” is called as described below withreference to FIG. 22.

In an alternative implementation to the method represented in FIG. 20,the computational operation represented by block 2008 may be omitted.Rather than computing a difference gather from the forward and backwardextrapolated wavefields, difference amplitudes may be calculate for eachtime of the series of time windows after block 2009, as described abovewith reference to FIG. 15.

FIG. 21 shows a flow-control diagram of the routine “compute maximumenergy difference” called in block 2010 of FIG. 20. In block 2101,amplitude differences in a time window W_(m) are identified. In block2102, energy differences are calculated for each amplitude difference inthe time window W_(m), as described above with reference to FIG. 12B andFIG. 15. In block 2103, a maximum energy difference for the time windowW_(m) is identified as described above with reference to Equation (12).

FIG. 22 shows a flow-control diagram of the routine “wavefieldseparation” called in block 2015 of FIG. 20. A for-loop beginning withblock 2201 repeats the computational operations represented by blocks2202-2209 for each time window. A for-loop beginning with block 2202repeats the computational operations represented by blocks 2203-2205 foreach trial depth. In block 2203, a set of maximum energy differences isformed as described above with reference to FIG. 13. In block 2204, whenthe trial depth index n does not equal the number of trial depths,control flows to block 2205 in which the trial depth index isincremented and the operation represented by block 2203 is repeated.Otherwise, control flows to block 2206 and a peak trial depth isdetermined as described above with reference to Equation (13). In block2207, receiver coordinates associated with the peak trial depth aredetermined as described above with reference to FIG. 14. In decisionblock 2208, when the time window index in does not equal the number oftime windows in the time window series M, control flows to block 2209and the time window index is incremented and the operations representedby blocks 2202-2208 are repeated. In block 2209, a routine “computevertical particle velocity wavefield” is called to compute anapproximate vertical particle velocity wavefield. In block 2210,separate wavefields are computed from the measured pressure wavefieldreceived in block 2001 of FIG. 20 and the approximate vertical particlevelocity wavefield.

FIG. 23 shows a flow-control diagram of the routine “compute verticalparticle velocity wavefield” called in block 2209 of FIG. 23. In block2301, an approximate frozen free-surface profile that represents afrozen in time profile of the free-surface above a streamer is computedas described above with reference to FIG. 16A. In block 2302, anapproximate frozen free-surface extension is computed as described withreference to FIG. 16B and Equations (15)-(21). A for-loop beginning withblock 2303 repeats the computational operations represented by blocks2304-2307 for each receiver. In block 2304, frozen free-surfacewavefield reflectivity is computed as described above with reference toEquation (22) and shown in FIG. 17. In block 2305, a pressure gradientis computed as described above with reference to Equation (23) when thesource is located shallower than the streamer or computed as describedabove with reference to Equation (24) when the source is located deeperthan the streamer. In block 2306, a vertical particle velocity iscomputed as describe above with reference to Equation (25). In decisionblock 2307, when a vertical particle velocity has not been computed forthe full set of receivers that generated the measured pressure wavefieldreceived in block 2001 of FIG. 20, the operations represented by blocks2304-2306 are repeated.

The mathematical equations and gathers presented above are not, in anyway, intended to mean or suggest an abstract idea or concept. Insteadthe mathematical equations and gathers described above represent actualphysical and concrete concepts and properties of materials that are inexistence. The mathematical equations and methods described above areultimately implemented on physical computer hardware, data-storagedevices, and communications systems in order to obtain results that alsorepresent physical and concrete concepts of materials that are inexistence. For example, as explained above, a pressure wavefieldemanating from an actual subterranean formation after being illuminatedwith an acoustic signal is composed of actual physical pressure wavesthat are sampled using physical and concrete pressure sensors. Thepressure sensors in turn produce physical electrical or optical signalsthat encode pressure wavefield data that is physically recorded onphysical data storage devices and undergoes computational processingusing hardware as describe above to obtain up-going wavefield data thatrepresents physical and concrete up-going pressure and vertical particlevelocity wavefields. The up-going wavefield data may be displayed, orsubjected to further seismic data processing, in order to interpret thephysical structure and composition of the subterranean formation, suchas in monitoring production of an actual hydrocarbon deposit within thesubterranean formation.

Note that in certain implementations, the computational operationsrepresented blocks 2004-2007 may be executed in parallel as shown inFIG. 20. In other implementations, the computational operationrepresented by block 2004 may be executed before the computationaloperation represented by block 2006 followed a transformation of thegathers obtained in blocks 2004 and 2006 from the f-k domain to the s-tdomain in block 2401 as shown in FIG. 24A. In still of theimplementations, the computational operation represented by block 2004may be executed after the computational operation represented by block2006 followed a transformation of the gathers obtained in blocks 2004and 2006 from the f-k domain to the s-t domain in block 2401 as shown inFIG. 24B.

FIG. 25 shows an example of a computer system programmed to executeefficient methods of computing approximate vertical particle velocitywavefields and separate up-going and down-going pressure wavefieldsbased on measured pressure wavefields and therefore represents ageophysical-analysis data-processing system. The internal components ofmany small, mid-sized, and large computer systems as well as specializedprocessor-based storage systems may be described with respect to thisgeneralized architecture, although each particular system may featuremany additional components, subsystems, and similar, parallel systemswith architectures similar to this generalized architecture. Thecomputer system contains one or multiple central processing units(“CPUs”) 2502-2505, one or more electronic memories 2508 interconnectedwith the CPUs by a CPU/memory-subsystem bus 2510 or multiple busses, afirst bridge 2512 that interconnects the CPU/memory-subsystem bus 2510with additional busses 2514 and 2516, or other types of high-speedinterconnection media, including multiple, high-speed serialinterconnects. The busses or serial interconnections, in turn, connectthe CPUs and memory with specialized processors, such as a graphicsprocessor 2518, and with one or more additional bridges 2520, which areinterconnected with high-speed serial links or with multiple controllers2522-2527, such as controller 2527, that provide access to variousdifferent types of computer-readable media, such as computer-readablemedium 2528, electronic displays, input devices, and other suchcomponents, subcomponents, and computational resources. The electronicdisplays, including visual display screen, audio speakers, and otheroutput interfaces, and the input devices, including mice, keyboards,touch screens, and other such input interfaces, together constituteinput and output interfaces that allow the computer system to interactwith human users. Computer-readable medium 2528 is a data-storagedevice, including electronic memory, optical or magnetic disk drive, USBdrive, flash memory and other such data-storage device. Thecomputer-readable medium 2528 can be used to store machine-readableinstructions that encode the computational methods described above andcan be used to store encoded data, during store operations, and fromwhich encoded data can be retrieved, during read operations, by computersystems, data-storage systems, and peripheral devices.

FIGS. 26A-26B show simulation results in calculating an approximation toa frozen free-surface. FIG. 26A shows a total pressure wavefieldobtained from an actual numerical simulation. Horizontal axis 2602represents channel (i.e., trace) numbers and vertical axis 2604represents time. Dashed hyperbolic-shaped curves 2606 and 2608 identifylower and upper the hyperbolic-shaped time series boundaries. A seriesof time windows was applied to pressure wavefield data within theboundaries 2606 and 2608 to compute an approximate free-surfacerepresented in FIG. 26B. FIG. 26B shows as a true free-surfacerepresented by solid-line curve 2610 and an approximate frozenfree-surface profile represented by dashed-line curve 2612. Horizontalaxis 2614 represents distance along a streamer and vertical axis 2616represents depth. Methods described above were applied to the syntheticpressure wavefield located between the boundaries 2606 and 2608 tocompute the approximate frozen free-surface profile 2612, which shows aclose approximation to the true free-surface distances below about 4500meters but still tracks the overall profile of the true free-surface fordistances greater than about 4500 meters.

Although the above disclosure has been described in terms of particularimplementations, it is not intended that the disclosure be limited tothese implementations. Modifications within the spirit of thisdisclosure will be apparent to those skilled in the art. For example,any of a variety of different implementations may be obtained by varyingany of many different design and development parameters, includingprogramming language, underlying operating system, modular organization,control structures, data structures, and other such design anddevelopment parameters.

The method described above may be implemented in real time while amarine survey is being conducted or subsequent to completion of themarine survey. The up-going and down-going wavefield gathers computed asdescribed above form a geophysical data product indicative of certainproperties of a subterranean formation. The geophysical data product mayinclude processed seismic data and may be stored on a computer-readablemedium as described above. The geophysical data product may be producedoffshore (i.e. by equipment on the survey vessel 102) or onshore (i.e.at a computing facility on land) either within the United States or inanother country. When the geophysical data product is produced offshoreor in another country, it may be imported onshore to a data-storagefacility in the United States. Once onshore in the United States,geophysical analysis may be performed on the data product.

It is appreciated that the previous description of the disclosedembodiments is provided to enable any person skilled in the art to makeor use the present disclosure. Various modifications to theseembodiments will be readily apparent to those skilled in the art, andthe generic principles defined herein may be applied to otherembodiments without departing from the spirit or scope of thedisclosure. Thus, the present disclosure is not intended to be limitedto the embodiments shown herein but is to be accorded the widest scopeconsistent with the principles and novel features disclosed herein.

1. A method comprising: computing forward and backward extrapolatedgathers based on a pressure wavefield gather for each trial depth of aseries of trial depths, the pressure wavefield gather generated byreceivers of a seismic data acquisition system located beneath afree-surface of a body of water; computing an approximate frozenfree-surface profile of the free-surface based on the forward andbackward extrapolated gathers; computing an approximate verticalparticle velocity wavefield gather based on the pressure wavefieldgather and the approximate frozen free-surface profile; and computingone of separate up-going and down-going vertical particle velocitywavefield gathers based on the pressure wavefield gather and theapproximate vertical particle velocity wavefield gather.
 2. The methodof claim 1, wherein computing the approximate frozen free-surfaceprofile of the free-surface based on the forward and backwardextrapolated gathers further comprises: for each trail depth, computinga set of maximum energy differences for each time window of a series oftime windows applied to the forward and backward extrapolated gathers;and for each time window, computing a peak energy from the sets ofmaximum energy differences computed for each trial depth.
 3. The methodof claim 2, wherein computing the set of maximum energy differences foreach time window of the series of time windows further comprises:computing a difference gather based on the pair of forward and backwardextrapolated gathers associated with each trial depth; and computing theset of maximum energy differences for each time window of a series oftime windows applied to the difference gathers.
 4. The method of claim2, wherein computing the set of maximum energy differences for each timewindow of the series of time windows further comprises: computing energydifferences for each time window applied to the same time interval ofthe forward and backward extrapolated gathers associated with each trialdepth; and computing a set of maximum energy differences for each timewindow of a series of time windows applied to the forward and backwardextrapolated gathers.
 5. The method of claim 2, wherein computing thepeak energy of the sets of maximum energy differences further comprisesidentifying a maximum of the sets of maximum energy differences.
 6. Themethod of claim 1, wherein computing the approximate frozen free-surfaceprofile of the free-surface further comprises interpolating theapproximate frozen free-surface profile of the free-surface based onpeak energy differences between the forward and backward extrapolatedgathers.
 7. The method of claim 1, wherein computing the gather ofapproximate vertical particle velocity wavefield data further comprises:computing frozen free-surface wavefield reflectivity based on theapproximate frozen free-surface profile; computing a pressure wavefieldgradient based on the frozen free-surface wavefield reflectivity and thepressure wavefield data; and computing the gather of approximatevertical particle velocity wavefield data from the pressure wavefieldgradient.
 8. The method of claim 1 executed on a programmable computerprogrammed to execute the method.
 9. The method of claim 1 furthercomprises storing the gather of approximate vertical particle velocitywavefield data in one or more data-storage devices.
 10. The method ofclaim 1, wherein the wavefield gathers form a geophysical data product,further comprising recording the geophysical data product on a physical,non-volatile computer-readable medium suitable for importing onshore.11. The method of claim 10, further comprising performing geophysicalanalysis onshore on the geophysical data product.
 12. The method ofclaim 1, computing the approximate frozen free-surface profile furthercomprises: computing a frozen-free-surface extension from a free-surfacemodel based on parameters associated with weather conditions measured atthe time of the marine survey; and combining the frozen-free-surfaceextension with the approximate frozen free surface profile.
 13. Acomputer system that performs wavefield separation, the systemcomprising: one or more processors; one or more data-storage devices;and a routine stored in one or more of data-storage devices and executedby the one or more processors, the routine directed to computing forwardand backward extrapolated gathers based on a pressure wavefield gatherfor each trial depth of a series of trial depths; computing anapproximate frozen free-surface profile of the free-surface based on theforward and backward extrapolated gathers; computing an approximatevertical particle velocity wavefield gather based on the pressurewavefield gather and the approximate frozen free-surface profile; andcomputing one of separate up-going and down-going pressure and verticalparticle velocity wavefield gathers based on the pressure wavefieldgather and the approximate vertical particle velocity wavefield gather.14. The computer system of claim 13, wherein computing the approximatefrozen free-surface profile of the free-surface based on the forward andbackward extrapolated gathers further comprises: for each trail depth,computing a set of maximum energy differences for each time window of aseries of time windows applied to the forward and backward extrapolatedgathers; and for each time window, computing a peak energy from the setsof maximum energy differences computed for each trial depth.
 15. Thecomputer system of claim 14, wherein computing the set of maximum energydifferences for each time window of the series of time windows furthercomprises: computing a difference gather based on the pair of forwardand backward extrapolated gathers associated with each trial depth; andcomputing the set of maximum energy differences for each time window ofa series of time windows applied to the difference gathers.
 16. Thecomputer system of claim 14, wherein computing the set of maximum energydifferences for each time window of the series of time windows furthercomprises computing energy differences for each time window applied tothe same time interval of the forward and backward extrapolated gathersassociated with each trial depth; and computing the set of maximumenergy differences for each time window of a series of time windowsapplied to the forward and backward extrapolated gathers.
 17. Thecomputer system of claim 14, wherein computing the peak energy of thesets of maximum energy differences further comprises identifying themaximum of the sets of maximum energy differences.
 18. The computersystem of claim 13, wherein computing the approximate frozenfree-surface profile of the free-surface further comprises interpolatingthe approximate frozen free-surface profile of the free-surface based onpeak energy differences between the forward and backward extrapolatedgathers.
 19. The computer system of claim 13, wherein computing thegather of approximate vertical particle velocity wavefield data furthercomprises: computing frozen free-surface wavefield reflectivity based onthe the approximate frozen free-surface profile; computing a pressurewavefield gradient based on the frozen free-surface wavefieldreflectivity and the pressure wavefield data; and computing the gatherof approximate vertical particle velocity wavefield data from thepressure wavefield gradient.
 20. The computer system of claim 13 furthercomprises storing the gather of approximate vertical particle velocitywavefield data in the one or more data-storage devices.
 21. The computersystem of claim 13, wherein the wavefield gathers form a geophysicaldata product, further comprising recording the geophysical data producton a physical, non-volatile computer-readable medium suitable forimporting onshore.
 22. The computer system of claim 21, furthercomprising performing geophysical analysis onshore on the geophysicaldata product.
 23. A physical computer-readable medium havingmachine-readable instructions encoded thereon for enabling one or moreprocessors of a computer system to perform the operations of computingforward and backward extrapolated gathers based on a pressure wavefieldgather for each trial depth of a series of trial depths; computing anapproximate frozen free-surface profile of the free-surface based on theforward and backward extrapolated gathers; computing an approximatevertical particle velocity wavefield gather based on the pressurewavefield gather and the approximate frozen free-surface profile; andcomputing one of separate up-going and down-going pressure and verticalparticle velocity wavefield gathers based on the pressure wavefieldgather and the approximate vertical particle velocity wavefield gather.24. The medium of claim 23, wherein computing the approximate frozenfree-surface profile of the free-surface based on the forward andbackward extrapolated gathers further comprises: for each trail depth,computing a set of maximum energy differences for each time window of aseries of time windows applied to the forward and backward extrapolatedgathers; and for each time window, computing a peak energy from the setsof maximum energy differences computed for each trial depth.
 25. Themedium of claim 24, wherein computing the set of maximum energydifferences for each time window of the series of time windows furthercomprises: computing a difference gather based on the pair of forwardand backward extrapolated gathers associated with each trial depth; andcomputing the set of maximum energy differences for each time window ofa series of time windows applied to the difference gathers.
 26. Themedium of claim 24, wherein computing the set of maximum energydifferences for each time window of the series of time windows furthercomprises: computing energy differences for each time window applied tothe same time interval of the forward and backward extrapolated gathersassociated with each trial depth; and computing the set of maximumenergy differences for each time window of a series of time windowsapplied to the forward and backward extrapolated gathers.
 27. The mediumof claim 24, wherein computing the peak energy of the sets of maximumenergy differences further comprises identifying the maximum of the setsof maximum energy differences.
 28. The medium of claim 23, whereincomputing the approximate frozen free-surface profile of thefree-surface further comprises interpolating the approximate frozenfree-surface profile of the free-surface based on peak energydifferences between the forward and backward extrapolated gathers. 29.The medium of claim 23, wherein computing the gather of approximatevertical particle velocity wavefield data further comprises: computingfrozen free-surface wavefield reflectivity based on the the approximatefrozen free-surface profile; computing a pressure wavefield gradientbased on the frozen free-surface wavefield reflectivity and the pressurewavefield data; and computing the gather of approximate verticalparticle velocity wavefield data from the pressure wavefield gradient.30. The medium of claim 23 executed on a programmable computerprogrammed to execute the method.
 31. The medium of claim 23 furthercomprises storing the gather of approximate vertical particle velocitywavefield data in one or more data-storage devices.
 31. The medium ofclaim 22, wherein the wavefield gathers form a geophysical data product,further comprising recording the geophysical data product on a physical,non-volatile computer-readable medium suitable for importing onshore.32. The medium of claim 31, further comprising performing geophysicalanalysis onshore on the geophysical data product.